PRELIMINARY REPORT on the CAUSAPSCAL EAST AREA NARY REPORT on Glitz CAUSAPSCAL EAST A114
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GM 31984 PRELIMINARY REPORT ON THE CAUSAPSCAL EAST AREA NARY REPORT ON glitz CAUSAPSCAL EAST A114 AtergEtpu. Go QUEBEC C. W. Stearn October 1958 Ministere des Richesses Naturelles, Québec SERVICE DE LA DOCUMENTATION TECHNIQUE Date: 30 AOU 1976 No GM: PA;fitMINARY REPORT ON THE CAus,APsCAL EAST AREA MATA1?EUTA CO. QUEBEC C. W. Stearn INTRODUCTION The east half of the Causapscal area was mapped by the writer during the summer of 1958. The area lies largely on the east side of the Matapedia River near the base of the Gaspe Peninsula. It is bounded on the south by latitude 48 deg. 15', on the north by latitude 48 deg. 30' on the west by longitude 67 deg. 15', and on the east by longitude 6? deg. 00', and is about 200 square miles in area. Included within the area mapped are large parts of Casault, Lepage, Laverendrys, and Casup— scull townships and small parts of Biala, Assematquagan, anis. Natalia townships. The area is easily reached from all parts of Quebec by provincial highway No. 6, a paved road that passes through the Matapedia valley. From this artery gravel roads give ready access to nearly all parts of the region. Much of the area is farm land but the northeastern third is covered with dense woods. Numerous lumber roads and old trails traverse this wooded part in all directions but only a few are maintained in a condition that permits car travel. The main Canadian National Railway line from Montreal to Halifax follows the Matapedia valley through the southwestern part of the area. The land surface is a dissected upland. From points of vantage, such as the Casault Fire Tower which is built on the highest hill (1870 ft.), it appears to be formed of low, roiling hills with little relief. 2 However, into this upland surface the rivers and their major tributaries have cut valleys up to 400 feet deep producing a maximum relief in the urea of about 1500 feet. Most of the bedrock exposures are in stream valleys for the gently sloping uplands are heavily covered with mantle and bush. All the streams flow into the Matapedia River which traverses the southwestern part of the area. The upper part of its valley is broad and open but near Ste. Florence the valley becomes narrow and the sides steep. The Causapsœl River flows south and then west to join the Matapedia at the town of Causapseal. The best outcrops of bedrock occur along this river and its major tributariess Ruis. Huit Milles, Ruis. Petit Huit Mille a, Ruis. Quatre Milles, Ruis. Petit Quatre Milles, and Ruis. Trois Milles. The northern boundary of the area crosses a region of low relief where water has accumulated in Lakes Casuult and Huit Milles and in extensive swamps along the south branch of the Causapscel River. GF:Iilf4RAL U4LQG$ General Statement The Causapscal Last Area is underlain by bedrock of Silurian and Devonian age. These sandstones, siltstones, slates, and limestones consitute a section over 20,000 feet thick. A layer of intermediate volcanic rocks about 700 feet thick is intercalated in the slates in the southern part of the area. The sedimentary and volcanic rocks were deformed in the Devonian period into broad folds and broken along high angle faults. 3 A small dike was intruded into the Devonian sedimentary rocks after the folding. Deposits of Pleistocene age are not thick except in the Matapedia valley but scattered erratic boulders indicate that the Laurentide ice sheet completely covered the area. Table of Formation .. Pleistocene Ice contact drift, minor till, erratics. Middle Devonian Mork River - Benel formati x - 12,000 ft. Grey sandstone, red sandstone, siltstone, calcareous siltstone, minor conglomerate. fault Middle and/or Fortin Slate - thickness unknown Lower Devonian Slate, phyllitic slate, thin beds of sandstone Ste. Marguerite member - amygdaloidal and compact andesitic volcanics, minor breccia. Lower Devonian Grand Greve Siltetone - 3,500 ft. Calcareous siltstone, silty limestone. Cave Bon Asti Limeptpp - 2,500 ft. Argillaoeous limestone, minor silty limestone, siltstone. .- ... 00 00 ! Silurian St. Leon Siltetone - 5,000 ft. Calcareous siltstone, minor sandstone. St. Leon Siltstonf The St. Leon siltstone is exposed in the crests of two anticlines which plunge in opposite directions. In these structures approximately the upper 2,000 feet of the formation is exposed. Most of the formation is greenish grey, calcareous siltstone in thick or thin beds which weather medium grey and shades of orangish grey. Intercalated with the siltstone are minor beds of greenish grey, medium and fine grained sandstone. The bed& ng planes show flow casts in some localities but cross bedding, ripple mark, and other evidence of shallow water deposition is lacking. 4 Associated Development's Causapscal No. 1 well is coring a fine section of the St. Leon. The well was started about 2,000 feet stratigraphically below the top of the formation and by September 1958 had penetrated 4,200 feet of these beds with only minor changes in lithology. This well has established that the St. Leon is at least twice as thick in the Causapscal area as was estimated by Crickmay for the Lake latapedia area to the north. A coarse fracture cleavage is evident in most outcrops of this unit. The only fossils found in the St. Leon siltstones were a few spocimens of the graptolite Monoaraetus. On the basis of similar fossils the formation has previously been dated as Middle Silurian but it is possible that the upper part is Late Silurian in age for it is apparently conformable with the Cape Bon Ami limestone. Cane Bon Ami Limestone The contact of the Cape Bon Ami with the St. Leon is not exposed in the Causapscal East Area but no structural discordance le apparent between the beds of the two formations. The Cape Bon Ami for. oration is composed largely of dark grey, argillaceous, and locally silty limestone, typically closely cleaved and slaty in the more argillaceous layers. Bedding is commonly difficult to detect but where the beds are defined in a large outcrop they are two to three feet thick. A thinner lamination may also be present. In a few outcrops the beds have been greatly contorted by movement in the sediment while it wag still unconsol- idated but generally the beading is even and regular. A dark grey, non- calcareous siltstone unit about 100 feet thick occurs near the top of the formation. Near Rule. Huit Mille this siltstone is overlain by about 10 feet of light grey sandy rock that is possibly tuffaceous. This distinctive horizon could be traced over a limited area but does not seem to be regionally distributed. The thickness of this formation is difficult to compute from its dips and width of outcrop for it is cross folded in most of the area. It is estimated to be about 2,500 feet thick. Along the southern belt of outcrop in the Causapscal East area the Cape Bon Ani stands almost vertical and its outcrop widt3:1 is less than 1,000 feet. Flowage of this unit, and the overlying Grand Greve into the crest of the anticline to the north is presumed to have taken place for there is little evidence of faulting. The only fossils found in these limestones are sn,]1 brachiopods and these are very rare. More extensive fossil collections from other areas have been dated by paleontologists as Early Devonian in age. Grand Greve Siltstone The Grand Greve si:tstone outcrops in a southern linear belt extending east and west from the southern outskirts of Causapscal, and in a northern, 3-shaped belt. In the southern belt dips are steeply south, vertical, or overturned toward the north but in the northern belt dips are gentle. The formation is composed predominantly of calcareous silt- stones which are interbedded with silty limestones. Most of the rocks placed in this formation react sluggishly to dilute hydrochloric acid, easily scratch glass, and weather to a non-calcareous, light grey rubble whose constituent fragments, although leached of carbonate entirely, are still coherent. The lower part of the Grand Greve formation is banded with thin, light grey, silt-rich layers. This banding and thin bedding 6 have been used as criteria to distinguish the Grand Greve from the Cape Bon Ami. Small outcrops may be difficult to assign to one or other of these two formations without detailed study of their lithology especially where the Grand Greve has been sheared and developed the closely spaced cleavage more typical of the Cape Bon Ami. Generally the spacing of the cleavage planes is much closer in the latter. On vertical weathered surfaces of the Grand Greve formation closely spaced silty laminae are etched into relief. The lower contact is gradational but can generally be placed within a few hundred feet where argillaceous limestone or dark grey, non,. calcareous siltstone of the Cape Bon Ami changes to banded calcareous siltstone. The Grand Greve siltstone passes upward through an alternation of beds into the York River formation. The upper contact is placed for mapping purposes at the appearance of the first thick sandstone bed. Although this procedure places many beds of Grand Greve lithology in the York River formation, the contact can only be mapped on this basis. The Grand Greve siltstone is about 3,500 feet thick below the falls of the Causapscal River but in the southern belt it appears to have been tectonically thinned on the limb of a partly overturned anticline so that its outcrop width is only 2,000 feet. On Ruis. Trois Milles the Grand Greve is so thin and structurally disturbed that a fault is postulated between it and the York River-Koppel unit.